Ichnology of the Miocene Güneyce Formation (Southwest Turkey): Oxygenation and Sedimentation Dynamics

JAN KRESTEN NIELSEN1, MUHİTTİN GÖRMÜŞ2, KUBİLAY UYSAL2 & SÜVEYLA KANBUR2

1 Statoil ASA, Development and Production Norway, Field Development, P.O. Box 273, NO-7501 Stjørdal, Norway (E-mail: [email protected]) 2 Süleyman Demirel University, Department of Geological Engineering, TR−32260 Isparta, Turkey

Received 07 December 2010; revised typescripts received 18 March 2011 & 22 May 2011; accepted 28 May 2011

Abstract: Th e Güneyce Formation is well exposed in the Lake District of southwestern Turkey. It was deposited in the early Miocene in the Neotethys ocean and contains a large variety of trace fossils. Th e following ichnotaxa were recognized: Chondrites intricatus, C. targionii, ?Cosmorhaphe isp., Helminthopsis isp., Helminthorhaphe fl exuosa, Lorenzinia isp., Naviculichnium marginatum, ?Nereites isp., Ophiomorpha rudis, ?Phycosiphon incertum, Planolites beverleyensis, cf. Rhizocorallium isp. and Th alassinoides suevicus. Th ere is a lateral trend from proximal turbiditic successions to distal low-oxygen shaly mudstone. Ophiomorpha rudis ichnosubfacies, Paleodictyon ichnosubfacies of the Nereites ichnofacies and Zoophycos ichnofacies were identifi ed.

Key Words: trace fossils, turbidites, ichnofacies, oxygenation, Neotethys

Miyosen Yaşlı Güneyce Formasyonu (GB Türkiye) İz Fosilleri: Oksijenleşme ve Sedimantasyon Dinamiği

Özet: Güneyce Formasyonu çökel dizilimleri güneybatı Türkiye’de Göller Yöresinde önemli yüzeylenmeler vermektedir. Çökelim, Neotetis Okyanusu’nda erken Miyosen zamanında gerçekleşmiştir. Formasyon içerisinde belirlenen iz fosiller şunlardır: Chondrites intricatus, C. targionii, ?Cosmorhaphe isp., Helminthopsis isp., Helminthorhaphe fl exuosa, Lorenzinia isp., Naviculichnium marginatum, ?Nereites isp., Ophiomorpha rudis, ?Phycosiphon incertum, Planolites beverleyensis, cf. Rhizocorallium isp. ve Th alassinoides suevicus. İstift e, yakınsak turbiditik istifl erden düşük oksijenli şeylli çamurtaşına yanal geçişler bulunmaktadır. Ayrıca, formasyonda Ophiomorpha rudis, Paleodictyon ve Zoophycos iknoaltfasiyesleri tanımlanmıştır.

Anahtar Sözcükler: İz fosiller, türbidit, iknofasiyes, oksijenleşme, Neotetis

Introduction (Burdur) (Figure 1). Th e Triassic to Early Cretaceous Isparta Çay Formation, comprising radiolarite chert Th e geology of the Isparta Angle in southwestern and platy and turbiditic limestones, is erosively and Turkey is structurally complex. Various allochthonous unconformably overlain by Miocene formations: (Antalya and Lycian nappes) and autochthonous units have been recognized (e.g., Poisson 1967; the Karabayır, Güneyce and Gökdere formations, Gutnic et al. 1979; Poisson et al. 1983; Yalçınkaya which were formed in a regionally large basin. Th e et al. 1986, Yalçınkaya 1989; Şenel 1997). Th ey siliciclastic successions of the Güneyce Formation comprise Mesozoic and Palaeogene successions of are characterized by abundant trace fossils. In the Neotethys, which are commonly unconformably addition to the microfossil content, they can provide overlain by younger deposits (see Nielsen et al. 2010 complementary data about the palaeoenvironment. and references therein). Th is is also recognized in the For this reason, the Güneyce Formation is of areas of Dereboğazı (Isparta), Ağlasun and Sagalassos particular interest because it extends laterally for

391 ICHNOLOGY OF THE MIOCENE GÜNEYCE FORMATION, SW TURKEY

Bulgaria Black Sea Georgia

İstanbul Ankara

Turkey Isparta

Aegean Sea Aegean Antalya Adana

Cyprus Syria Mediterranean Sea

ei Qa

Isparta SAVKÖY

Mzd plQ g 1 plQ ei LAKE g plQ GÖLCÜK g AK SU Mza1 F Mza2 AU LT

mig plQ g

mi go Mt. AKDAĞ Mzl2 2 mi 4 k Sagalassos Mza2 Mz Mz l2 l2 mi 3 k Ağlasun Mzd Mzl1 Qa

Q a migo plQc Quaternary city mi g Miocene mik plQg eoli Pliocene-Quaternary village ei Eocene-Oligocene

palk Palaeocene Mzl2 Lycian Nappes 1 sample locality. Mza2 Mz l1 Antalya Nappes Mza1 N thrust Mz d Davraz Limestone 5 km normal fault

Figure 1. Geological map of the study area within the Isparta Angle, Turkey. Localities of the Miocene Güneyce Formation are indicated by numbers (1–4). Modifi ed from Gutnic et al. (1979), Şenel (1997) and Nielsen et al. (2010).

392 J.K. NIELSEN ET AL.

many kilometres. Th e aim of this study is to provide (Akbulut 1980; Yalçın 1993; Görmüş & Hançer 1997). the fi rst overview of trace fossils from the Güneyce Among these, we only report the stratigraphical Formation. Th e presence of trace fossils is discussed in and ichnological data from the siliciclastic rocks of terms of palaeoenvironmental conditions in relation the Güneyce Formation (Figures 1 & 2). Previous to sedimentation dynamics, substrate consistency, records gave details of the other Miocene formations oxygenation and other parameters. (Yalçınkaya et al. 1986; Yalçınkaya 1989; Yalçın 1993; Yağmurlu 1994; Görmüş & Hançer 1997; Şenel 1997; Geological Setting Görmüş et al. 2001; Poisson et al. 2003). In the study area, Miocene formations include Th e name of the Güneyce Formation is derived the Karabayır, Güneyce and Gökdere formations from Güneyce village, southwest of Isparta

AGE LITHOLOGY

a alluvium Q c clastics QUATERNARY plQ CENOZOIC a2 g Gölcük volcanics Mz plQ s e TERTIARY PLIOCENE pp a l2 Lycian Nappes TRIASSIC talya N Mz n A a1 l1 Mz MESOZOIC Mz

go Gökdere F ormation mi MESOZOIC g Güneyce Formation 1-4 mi

k KarabayıF r ormation MIOCENE mi

CRETACEOUS Davras Limestone i İncesu Formation b eol Mz

TERTIARY Isparta Formation CENOZOIC EOCENE- OLIGOCENE i e JURASSIC

Koçtepe Formation k EOCENE TRIASSIC pal PALAEOCENE

Figure 2. Stratigraphical overview of Mesozoic and Cenozoic formations exposed in the Burdur and Isparta regions. Structural nappes are indicated by older units on top of younger ones. Stratigraphical levels of localities are indicated by rectangular symbols. From Nielsen et al. (2010).

393 ICHNOLOGY OF THE MIOCENE GÜNEYCE FORMATION, SW TURKEY

(Akbulut 1980). Rhythmical siliciclastic sediments bijugatus. Reworked Cretaceous nannofossils: Micula were identifi ed as ‘the Burdigalian fl ysch’ by decussate, from the Cretaceous/Palaeogene boundary: Gutnic et al. (1979). Th e Ağlasun Formation is a Aspidolithus parcus constrictus, Briantolithus sparsus, more recent synonym of the Güneyce Formation Litraphidites quadratus, Microrhabdulus attenuatus, (Yalçınkaya 1989; Karaman 1990). We prefer the Micula decussata, Prinsius bisulcus, Stradneria original formation name given by Akbulut (1980) crenulata, Th oracosphaera saxea and Watznaveria according to stratigraphical rules (Hedberg 1976). barnesae. Th e fossils of the entire Güneyce Formation Th e Güneyce Formation is exposed widely around indicate an early Miocene age, i.e., Aquitanian− İmrezi, Kışla, Darıören and Güneyce villages. Burdigalian−?Langhian age (Görmüş et al. 2001, Siliciclastic sediments are dominant and include 2004). Lithological characteristics and fossil contents various sedimentary facies such as (1) mudstone- of the Güneyce Formation indicate a transgressive to dominated facies; (2) sandstone-dominated facies; regressive succession, from shallower to open sea and (3) olistostromal facies; (4a) rhythmic heterolithic back to shallower palaeoenvironments. facies of sandstone and mudstone; (4b) carbonate facies; (5) pure sandstone facies; (6) coarse clastic- conglomerate facies (Görmüş et al. 2001). Th e Sedimentological Overview last two facies are distinguished as separate units: Overall the Güneyce Formation contains primary the Gökdere Formation (Yalçın 1993). Th e total sedimentary structures typical of turbidity current thickness of the Güneyce Formation is between deposits. Th is chapter gives a generalised overview 500−750 m, according to our fi eld observations. Th e of these deposits. Th e divisions Ta, Tb, Tc, Td and underlying contact with the Karabayır Formation is Te by Bouma (1962) have been widely used to conformable and interfi ngering is present. Pliocene describe turbiditic beds (e.g., Komar 1985; Talling and Quaternary volcanic rocks rest unconformably 2001; Sinclair & Cowie 2003; Bouma 2004; Schultz on the Miocene sediments, as in the palaeovalley & Hubbard 2005; Warchoł & Leszczyński 2009). located 2 to 3 km south of Savköy. Walker (1978) and Mutti (1992) found the Bouma divisions to be insuffi cient for classifi cation of coarse- Microfossils and nannofossils of the Güneyce grained beds, which may contain a broad spectrum Formation are listed below. Details about nannofossils of sediment types. For detailed facies analysis with and their reworking are compiled from Görmüş et al. genetic facies, Mutti (1992) recommended that the (2001, 2004). Planktonic foraminifera: Globigerina broadly descriptive divisions of Bouma (1962), Mutti sp., Globigerinoides sp., Globorotalia sp., G. cf. kugleri, & Ricci Lucchi (1972) and Walker (1978) should be Globoquadrina dehiscens, reworked Morozovella abandoned. In the present study, we consider the aequa, M. angulata. Benthic foraminifera: Bouma divisions adequate to capture the common Amphistegina sp., Lepidocyclina (Eulepidina) sp., sediment types in the Güneyce Formation. Th e Lepidocylina (Nephrolepidina) sp., Miogypsina sp., formation contains relatively well-sorted sandstones Miogypsinoides sp. and Operculina sp. Nannofossils: with a tabular and tapered geometry, which Braarudosphaera bigelowii, Calcidiscus sp., diff erentiate them from debrites (Amy et al. 2005). Cyclicargolithus abisectus, C. fl oridanus, Coccolithus pelagicus, Discoaster defl andrei, D. druggii, Four localities, typical of the Güneyce Formation Dictyococcites bisectus, Helicosphaera obliqua, in the Dereboğazı (1), Ağlasun (2, 3) and Sagalassos Sphenolithus belemnos, S. conicus, S. compactus, S. (4) areas, have been chosen for this study (Figures 1 dissimilis and S. moriformis. Reworked nannofossils & 2). Th e sedimentary successions in these localities from Eocene: Coronocyclus nitscens, Coccolithus formed in an open-sea environment during maximum pelagicus, Dictyococcites sp., Discoaster binodosus, sea level. Th ey cover approximately the central part of D. diastypus, D. gemmifer, D. salisburgensis, the formation (Figure 3). Detailed biostratigraphical D. multiradiatus, Ericsonia formosa, E. ovalis, studies are needed to verify whether the successions Sphenolithus radians, S. editus, Toweius eminens, are exactly coeval with each other. T. occultatus, T. pertusus, Tribrachiatus orthostylus, At locality 1 (Dereboğazı), the Güneyce Triquetrorhabdus carinutus and Zygrhablithus Formation succession consists of grey laminated or

394 J.K. NIELSEN ET AL.

NE SW

. . E ...... ~5 km ...... 4...... 3 ...... 2 . . C F ...... 1 ...... D...... B ...... A

Güneyce Formation overall grain size

frequency of erosive events dysoxic conditions ichnodiversity, density

depth of tiers

Figure 3. Palaeoenvironmental reconstruction of the Miocene Güneyce Formation. Isparta Çay Formation (A, B) including radiolarite chert (A) and turbiditic limestones (B). Karabayır Formation (C). Güneyce Formation (D). Gökdere Formation (E). Disconformity (F). Th e Güneyce Formation interfi ngers with the shallow-marine Karabayır Formation, and erosively superposes bedrocks of the Isparta Çay Formation. Localities indicated by numbers (1–4). massive shaly mudstones. Th ese can be interpreted as compaction. Th e sandstones may be overlain by indicators of low density turbidity current deposition laminated mudstone (division Td), forming couplets. and hemipelagic sedimentation (division Tde). At locality 4 (Sagalassos), the beds consist At locality 2 (Ağlasun), the Güneyce Formation commonly of sandstone and siltstone layers. Th e consists predominantly of sheet-like beds of coupled sandstone layers are massive or normal graded, silty sandstones and mudstones. Th e sandstones are typically 10−20 cm thick. Groove structures, which typically less than 5 cm thick, which is thinner than may be present on bedding planes, were formed at locality 3. Th e mudstones are laminated or massive by objects dragged along the sea fl oor. Th e graded (divisions Td and Te). sandstone layers represent the division Ta. Th ese are At locality 3 (Ağlasun), the succession contains overlain by parallel laminated sandstone layers less sandstone layers up to 10 cm thick, thicker than at than 25 cm thick assigned to division Tb. Cross- locality 2. Plane parallel laminae (division Tb) and laminated silty sandstone to siltstone (division Tc) cross laminae (division Tc) are common. Th e latter may be present at the top of the beds. may appear in silty sandstones. Flute casts may be As supported by laboratory experiments (e.g., present on bedding planes. Small wrinkle structures Middleton 1967; Parsons et al. 2002), the coarse- may rarely be present, indicating rapid loading and grained sediment was preferentially deposited

395 ICHNOLOGY OF THE MIOCENE GÜNEYCE FORMATION, SW TURKEY

proximally in the fan system. Th e fi ne grains tended up to 30 mm long. Th ey are commonly horizontally to travel further outwards. Th e overall grain size, bed or subhorizontally oriented to bedding and aff ected thickness and sand/shale ratio (Walker 1978) indicate by compaction. Th e branches do not cross-cut each that the succession at locality 4 formed proximally in other. the depositional system (intermediate fan), while the Remarks − Fu (1991) revised the ichnogenus other successions at localities 1, 2 and 3 formed more Chondrites, and here we follow her emendation of C. distally (outer fan). Nevertheless, the interpretation intricatus. In Turkey, the ichnospecies has been found of proximality presumes a generalised fan system. in deep-sea fan fringe deposits within the western fan Th e grain size and the bed thickness can vary laterally of the Miocene Cingöz Formation (Adana Basin), in local parts of the fan system. where the trace fossil assemblages are representative of the Nereites ichnofacies together with some features Material and Methods of the Skolithos and Cruziana ichnofacies (Uchman & Demircan 1999; Demircan & Yıldız 2007). Specimens Road sections were studied during the fi eldwork. of C. intricatus are also present in middle fan deposits Particular sections (localities 1 to 4) were investigated of the late Eocene Korudağ Formation within the further for primary sedimentary structures and trace Th race Basin, Turkey (Demircan & Uchman 2006; fossils. Th e scree material of these sections was also see Demircan 2008). Chondrites isp. has also been examined. Hand-picked samples were collected and a found in outer fan deposits of the middle−late Eocene selection of them is housed at the Jeoloji Mühendisliği Gaziköy Formation (Th race Basin) (Demircan & Bölümü, Süleyman Demirel University. Bertling Uchman 2006) and the Eocene Kırkgeçit Formation et al. (2006) gave an overview of morphological (Elazığ) (Özkul 1993). In the Sinop-Boyabat Basin, C. features relevant to trace fossil identifi cation, intricatus is present in the deep-marine fl ysch of the i.e. ichnotaxobases. Th eir recommendations for Maastrichtian−Palaeocene Akveren Formation and ichnotaxobases are followed here. the Eocene Kusuri Formation (Uchman et al. 2004).

Ichnology Chondrites targionii (Brongniart 1828) Bioturbation structures are absent to moderately Description − Th e burrow system of C. targionii is frequent in the Miocene Güneyce Formation (Figures slightly winding and has commonly slightly curved 4 & 5, Table 1). Th e ichnodiversity is low at localities branches. Th e individual branches are 2 to 4 mm 1 (Dereboğazı) and 4 (Sagalassos), whereas localities wide. Branching angles are acute. 2 and 3 (Ağlasun) are characterized by moderate ichnodiversity (Figure 3). Remarks − Chondrites targionii diff ers from C. intricatus by its commonly curved branches. For Cross-cuttings between the trace fossils are generally absent. Th e graphoglyptids are common at discussion of this ichnospecies see Fu (1991) and the localities 2 and 3, whereas they are rare at locality Uchman (1998). Th e ichnospecies is known from 4 (Table 1). Th ey occur on the sole of sandstones the Akveren and Kusuri formations (Uchman et al. and are preserved in convex hyporelief because of 2004). slight scouring and casting. Other trace fossils are preserved in full relief (see below). ?Cosmorhaphe isp. Description − ?Cosmorhaphe isp. has apparently only Chondrites intricatus (Brongniart 1823) one order of meanders. Th e trace fossil, which is Description − Chondrites intricatus is rare at locality preserved in convex hyporelief, is 2 mm wide and can 1 (Figure 4b). It is characterized by its branching be at least 18 cm long. burrow system composed of straight, unlined Remarks − Th e specimens are poorly preserved segments and consistent branching angle at 35 to 45°. and are therefore left in open nomenclature (Figure Th e individual branches are 0.5 to 1 mm wide and 4d). Cosmorhaphe and its ichnospecies have been

396 J.K. NIELSEN ET AL.

a b

d c

Pl H

e f Figure 4. Th e Güneyce Formation. (a) Road section (locality 1) through the Güneyce Formation (ne) and volcanoclastic deposits (v), looking southwards. Th e section is about 15 m high. (b) Chondrites intricatus (triangles). Locality 1. (c) Lorenzinia isp., hyporelief. Centres of trace fossils indicated by dashed lines. Locality 2. (d) ?Cosmorhaphe isp., poorly preserved hyporelief (triangles). Locality 2. (e) ?Helminthopsis isp., hyporelief (triangles). Locality 2. (f) Planolites beverleyensis (Pl) and Helminthopsis isp. (H). Locality 3. Scale bars 1 cm. summarized and discussed by Uchman (1998). Formation (Uchman & Demircan 1999; Demircan & Cosmorhaphe sinuosa (Azpeitia Moros 1933) is Toker 2003, 2004). C. sinuosa has also been found in present in the outer fan depositional lobes (fan fringe) the abyssal to lower slope palaeoenvironments of the of the eastern and western fans of the Miocene Cingöz Eocene Korudağ Formation (Demircan 2008).

397 ICHNOLOGY OF THE MIOCENE GÜNEYCE FORMATION, SW TURKEY

a b

c d

e f

Figure 5. Th e Güneyce Formation. (a) ?Nereites isp., full relief (triangles). Locality 3. (b) Th alassinoides suevicus, full relief (triangles). Locality 3. (c) Cf. Rhizocorallium isp., hyporelief. Locality 3. (d) Road section through turbiditic deposits, looking northwards. Stratigraphical top is to the left . Locality 4. Scale bar 40 cm. (e) Ophiomorpha rudis, full relief. Locality 4. (f) Naviculichnium marginatum, epichnial relief. Locality 4. Scale bars 1 cm, except for (d) with scale bar 40 cm.

398 J.K. NIELSEN ET AL.

Table 1. Overview showing the distribution of trace fossils at localities of the Miocene Güneyce Formation in the Dereboğazı, Ağlasun and Sagalassos areas.

Early Miocene Güneyce Formation Localities: 1 2 3 4 Chondrites intricatus (Brongniart 1823) + Chondrites targionii (Brongniart 1828) + + Cosmorhaphe isp. ? Helminthopsis isp. ++ + + Helminthorhaphe fl exuosa Uchman 1995 + Lorenzinia isp. ++ + Naviculichnium marginatum Książkiewicz 1977 + Nereites isp. ? ? Ophiomorpha rudis (Książkiewicz 1977) + + ++ Phycosiphon incertum Fischer-Ooster 1858 ? Planolites beverleyensis Billings 1862 ++ ++ + cf. Rhizocorallium isp. + Th alassinoides suevicus (Rieth 1932) +

Note: +, few specimens; ++, common; +++, abundant.

Helminthopsis isp. curvature pattern shows high amplitude irregular Description − Unbranched, irregularly winding meanders. horizontal burrows are preserved in convex Remarks − Th e curvature pattern resembles that hyporelief (Figure 4e, f). Crossings are absent. Th e described by Uchman (1995). Th e bulging turns of H. width is about 0.5 cm and the length is at least 25 cm. japonica (Tanaka 1970) are absent. Helminthorhaphe Remarks − In Turkey, the ichnogenus fl exuosa is known from the fan fringe deposits of Helminthopsis has been described from the abyssal the Eocene turbiditic Cingöz Formation (Uchman and slope deposits of the Eocene Korudağ Formation & Demircan 1999; Demircan & Toker 2004). Th e (Demircan 2008), and from the turbiditic fan ichnospecies has also been described from the deposits of the Eocene Cingöz Formation (Demircan Eocene Kusuri Formation (Uchman et al. 2004). & Toker 2003, 2004). Helminthopsis isp. is present in the Maastrichtian−Palaeocene fl ysch of the Akveren Lorenzinia isp. Formation, in the Sinop-Boyabat Basin (Uchman et al. 2004). Description − Lorenzinia isp. is a radiating graphoglyptid trace fossil consisting of short ridges in hyporelief (Figure 4c). Th ere may be about 10 ridges Helminthorhaphe fl exuosa Uchman 1995 placed in a circle, about 30 to 40 mm in diameter. Th e Description − Helminthorhaphe fl exuosa is present as ridges are of diff erent length, up to 13 mm long. One convex hyporeliefs on sandstones. It is horizontal and specimen of Lorenzinia isp. is seen to overlap another unbranched, 1 mm wide. Crossin gs are common. Th e specimen (Figure 4c).

399 ICHNOLOGY OF THE MIOCENE GÜNEYCE FORMATION, SW TURKEY

Remarks − Th e ichnogenus Lorenzinia was fan fringe deposits of the Cingöz Formation within the discussed by Uchman (1998). Demircan & Toker Adana Basin, southern Turkey (Uchman & Demircan (2003) recognized Lorenzinia pustulosa (Książkiewicz 1999; Demircan & Toker 2003). Th is ichnospecies 1977) in middle and outer fan deposits of the Miocene is also known from the outer fan deposits of the Cingöz Formation. Uchman et al. (2004) recorded middle−late Eocene Gaziköy Formation in the Adana Lorenzinia in siliciclastic fl ysch of the Eocene Kusuri Basin, and the middle fan deposits of the late Eocene Formation, in the Sinop-Boyabat Basin. Korudağ Formation (Th race Basin) (Demircan & Uchman 2006). Th e ichnospecies is also present in turbiditic channel fi ll and proximal lobe facies of Naviculichnium marginatum Książkiewicz 1977 the early−middle Eocene Kusuri Formation in the Description − Elongate depressions in epichnial Sinop-Boyabat Basin, northern Turkey (Uchman et preservation (Figure 5f). Th e length is between al. 2004). 25 and 46 mm, while the width is up to 15 mm. A marginal rim is present. Remarks − Naviculichnium marginatum has also ?Phycosiphon incertum Fischer-Ooster 1858 been found in Eocene deep-sea turbiditic deposits of Description − Th e specimens are horizontal spreite the Gorrondatxe section, North Spain (Rodríguez- structures of recurving U-lobes. Th e lobes consist Tovar et al. 2010). of a dark core and surrounding pale mantle. Th e individual lobes are about 7 mm in size. Th e specimens are poorly preserved in full relief. ?Nereites isp. Description − Poorly preserved specimens of ?Nereites Remarks − Th e ichnospecies Phycosiphon isp. occur as horizontal, loosely winding burrows incertum was discussed by Wetzel & Bromley (1994). (Figure 5a). Th e course is irregular and shows no Specimens of P. incertum occur in the Akveren overlap. Meniscate backfi ll is about 5 mm wide, Formation, in the Sinop-Boyabat Basin (Uchman et while the enveloped zone is thin and hardly visible. al. 2004). Specimens are also present in a diverse trace Th e specimens are therefore determined only at the fossil assemblage within the middle fan deposits of ichnogeneric level. the Korudağ Formation (late Eocene), Th race Basin. Th e trace fossil assemblage is typical of the Nereites Remarks − Th e ichnogenus Nereites was revised by ichnofacies (Demircan & Uchman 2006). Uchman (1995). Nereites isp. was found by Demircan & Uchman (2006) in middle fan deposits of the Eocene Gaziköy Formation. Uchman & Demircan Planolites beverleyensis Billings 1862 (1999) and Demircan & Toker (2004) observed Nereites irregularis (Schafh äutl 1851) in fan fringe Description − Planolites beverleyensis is present deposits of the Miocene Cingöz Formation. as horizontal ridges in hyporelief (Figure 4f). Th e ridges, which are unbranched, are 3 to 5 mm wide. Transverse cross-sections are semi-circular in outline. Ophiomorpha rudis (Książkiewicz 1977) Th e ridges are straight to slightly curved. Description − Specimens of Ophiomorpha rudis can Remarks − Th e ichnogenus Planolites and its be at least 55 cm long and 0.5−1.0 cm in diameter ichnospecies were revised by Pemberton & Frey (Figure 5e). Th e branching angle ranges from 40 to (1982). Specimens of P. beverleyensis have also 90°. Th e specimens, which are preserved as full relief, been recognized in the western turbiditic fan may cross-cut the packages of sandstones. Filling is complex of the Miocene Cingöz Formation in the structureless and sandy. Wall lining is discontinuous Adana Basin (Demircan & Toker 2003). Planolites in places. Th e orientation of O. rudis is oblique to isp. was recorded as a facies-crossing form in horizontal. shelf and slope deposits of the Eocene Korudağ, Remarks − Ophiomorpha rudis was revised by Kešan and Yenimuhacir formations (Th race Basin) Uchman (2009). It has been recorded in the deep-sea (Demircan 2008). Planolites isp. occurs also in the

400 J.K. NIELSEN ET AL.

Barremian−Cenomanian Çağlayan Formation, the lithology and the distribution of trace fossils within Coniacian−Campanian Yemişliçay Formation and the Güneyce Formation (Table 1). Th e basinward the Maastrichtian−Palaeocene Akveren Formation part of the Güneyce Formation, which is the most in the Sinop-Boyabat Basin (Uchman et al. 2004). fi ne-grained and distal to sediment source, is present at locality 1 (Figure 3). Th e bottom water had a low content of oxygen, that is dysoxic conditions. Th is cf. Rhizocorallium isp. is shown by the low diversity and density of trace Description − Cf. Rhizocorallium isp. occurs rarely as fossils. Also, Chondrites intricatus is characterized by hyporelief in the Güneyce Formation (Figure 5c). Th e its small size (Figure 4b). Recognition of low oxygen trace fossil is characterized by a horizontal spreite levels by the presence of Chondrites in low-diversity with lobate outline. Th e trace fossil, which consists assemblages and decreasing burrow size was shown of a spreite of fairly regular U-shaped laminae, is by Bromley & Ekdale (1984) and Savrda & Bottjer horizontally retrusive and is 2.5 cm wide. Th e length (1986). Ekdale & Mason (1988) proposed an oxygen- is 7.5 cm. Th e marginal tunnel is not visible. controlled trace-fossil model, showing a transition Remarks − Th e ichnogenus Rhizocorallium was from fodinichnia (e.g., Chondrites) through revised by Fürsich (1974). Larger specimens of pascichnia to domichnia-dominated assemblages, Rhizocorallium isp. occur in the western middle with increasing oxygen concentration. Th e observed fan deposits of the Miocene Cingöz Formation distribution of trace fossils in the Güneyce Formation (Demircan & Toker 2003). conforms to this model. Chondrites intricatus in the Güneyce Formation may be common in places where the soft substrate was particularly rich in hydrogen Th alassinoides suevicus (Rieth 1932) sulphide or methane. Considering these sources for Description − Th alassinoides suevicus is preserved in cultivating bacteria, Chondrites may be interpreted as full relief and displays mainly horizontally oriented an agrichnion (e.g., Fu 1991; Savrda 1992; Seilacher galleries (Figure 5b). Th e width is 0.8 to 20 mm and 2007), or specifi cally belonging to the tentative the margin is unlined and smooth. Th e junctions subcategory chemichnia (Bromley 1996). Seilacher between branches are Y-shaped and slightly enlarged. (1990) proposed the ‘deviated-well’ hypothesis Remarks − For discussion of Th alassinoides suevicus for interpreting such cases. Modern analogue see Fürsich (1973), Frey et al. (1978), Howard & Frey traces are formed by thyasirid bivalves exploring (1984) and Schlirf (2000). Th alassinoides isp. has chemosymbiotic sources (Dando & Southward 1986; been described from the turbiditic proximal facies of Dufour & Felbeck 2003; Seilacher 2007). Chondrites the Maastrichtian−Palaeocene Samanlık Formation, intricatus of the Güneyce Formation comprises the in the Kalecik region (Yıldız et al. 2000), and from the only preserved tier of burrows at locality 1. Th ey turbiditic middle fan deposits of the Miocene Cingöz were formed in the sea fl oor under quiet conditions, Formation in the Adana Basin (Uchman & Demircan without the impact from turbiditic deposition. Th e 1999; Demircan & Yıldız 2007). It also occurs in the trace fossils are therefore interpreted as representative shelf and slope deposits of the Eocene Korudağ and of the Zoophycos ichnofacies (see Seilacher 1967; Keşan formations in the Th race Basin (Demircan Bromley & Asgaard 1991). Chondrites intricatus has 2008). Th alassinoides suevicus has been found in the previously been recognized as a deep tier trace fossil, Maastrichtian−Palaeocene turbidite deposits of the for instance, in post-turbidite mud in the Upper Akveren Formation as well as in the Eocene Kusuri Cretaceous of Schliersee (Bavaria) and the Eocene Formation in the Sinop-Boyabat Basin (Uchman et of Florence (Tuscany) (Seilacher 2007). Chondrites al. 2004). has been interpreted as refl ective of both single- layer and multi-layer colonization, for example, in the Marnoso-arenacea Formation and associated Discussion shelf deposits (Uchman 1995). D’Alessandro et al. Th e Miocene successions in the Dereboğazı, Ağlasun (1986) recognized Chondrites as an opportunistic and Sagalassos areas show lateral variation in the form in the Eocene Saraceno Formation, Italy. Th e

401 ICHNOLOGY OF THE MIOCENE GÜNEYCE FORMATION, SW TURKEY

trace makers colonized the turbidite sediment and present in fan fringe and overbank deposits of the burrowed deeper into it over time. Wetzel & Uchman Paleodictyon ichnosubfacies, with a higher diversity (2001) investigated ichnofabrics in the Eocene (Uchman 2009). A similar occurrence is recognized Beloveža Formation (Poland) and showed that post- in the Güneyce Formation, at localities 2 and 3. event colonization of muddy turbidites occurred Th e occurrence of the Ophiomorpha rudis sequentially. Th e relative appearance of trace makers ichnosubfacies in the Kusuri Formation, Sinop- was particularly related to the re-established redox Boyabat Basin, is characterised by reduced trace- boundary. Trace makers of Chondrites penetrated fossil diversity and abundant O. annulata and O. down into turbiditic layers in the late stages of rudis. Th is occurrence is interpreted as related to colonization, when oxygenation in pore waters plant detritus supplied from a large fl uvio-deltaic became poor (Wetzel & Uchman 2001). system (Uchman et al. 2004). At present, there is not enough evidence to confi rm or disprove that such a Th ere is a higher diversity and density of setting existed during the deposition of the Güneyce trace fossils in localities 2, 3 and 4 at Ağlasun and Formation. Sagalassos (Figures 4 & 5, Table 1). Turbiditic sandy beds are common and refl ect abrupt periods of increased sedimentation rate. Th e oxygenation of the Conclusions bottom water was higher and various trace makers Th e environments of the Güneyce Formation were apparently thrived, as indicated by the number characterized by diff erential variation in background of pre-turbidite trace fossils. Th ese structures are sedimentation rates, rapid depositional events and assigned to the Paleodictyon ichnosubfacies of the oxygenation of bottom water. Th e trace fossils of Nereites ichnofacies (see Seilacher 1974). the Güneyce Formation are representative of the Th e turbiditic deposits at localities 2, 3 and 4 (Figure Zoophycos ichnofacies as well as the Paleodictyon 5d) became colonized by trace makers, forming post- ichnosubfacies and the Ophiomorpha rudis turbidite traces. For example, Th alassinoides suevicus ichnosubfacies of the Nereites ichnofacies. Th e formed as open burrow systems in the turbidite sand deposits of the Güneyce Formation were produced in and became fi lled with fi ne-grained background open-sea siliciclastic environments in the Neotethys sediment. Fodinichnia such as Th alassinoides Ocean. Lateral trends in the trace fossil distribution suevicus represent depositional conditions typical show that the infl uence of turbiditic currents and of the Cruziana ichnofacies. Th alassinoides suevicus oxygenation varied with the proximity to sediment also occurs in other ichnofacies of the marine realm. source. Ophiomorpha rudis is also present. Its wall lining was built by the trace makers to stabilize the open burrow system. Ophiomorpha rudis is characteristic of the Acknowledgements low-diverse O. rudis ichnosubfacies of the Nereites Th e senior author is grateful to the Jeoloji ichnofacies (Uchman 2001, 2009; Uchman et al. 2004; Mühendisliği Bölümü, Süleyman Demirel University, Nielsen et al. 2010). Th is ichnosubfacies may occur for hospitality. Prof.Dr. Alfred Uchman (Jagiellonian in channel and proximal lobe facies of deep-sea fans, University, Kraków) is thanked for critical comments or in thick beds formed in a deep-sea ramp setting. on the manuscript. Figures 1 and 2 are adapted from Th e trace fossil assemblage at locality 4 (Sagalassos) Nielsen et al. (2010) with kind permission from the has a low diversity and is therefore assigned to the editorial offi ce of the Bulletin of Geosciences and the O. rudis ichnosubfacies. In addition, O. rudis can be Czech Geological Survey.

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